1Instituto de Geociências, Universidade de São Paulo – São Paulo (SP), Brazil. E-mails: barbara.btoledo@usp.br,
vajanasi@usp.br, guribeirova@gmail.com *Corresponding author.
Manuscript ID: 20180040. Received on: 04/06/2018. Approved on: 08/16/2018.
ABSTRACT:The Socorro Batholith is one of the most expressive granite manifestations associated with the Neoproterozoic evolution in SE Brazil, occupying large areas (~1,200 km2) in the southern portion of the Socorro-Guaxupé Nappe. A U-Pb zircon SHRIMP dating program was developed to determine the ages of the main components of this batholith, identified in previous detailed mapping projects. High-K calc-alkaline (HKCA) porphyritic biotite-hornblende granites with relatively low (60–67 wt%) SiO2 are the most voluminous component of this and other large “syn-tectonic” batholiths in the SGN (Água Limpa and Pinhal-Ipuiúna) and neighboring domains located south of it in the Apiaí and São Roque Domains of the Ribeira Fold Belt. Two samples collected in widely separated localities at the northern and southern part of the Socorro batholith yield similar ages of magmatic crystallization, respectively 610.1 ± 7.0 and 608.3 ± 6.6 Ma. A more fractioned (> 72 wt% SiO2) granite reported in the literature as related to a younger event (“Socorro II magmatism”, as opposed to the previous “Socorro I” HKCA granites) yield a precise age that is clearly older (624.4 ± 3.6 Ma), and contemporary to anatectic granites and migmatites that were produced during a prolonged period of high-grade metamorphism (635–605 Ma) that affected the SGN. Our data thus indicates that at least part of the HKCA magmatism that constitutes the Socorro batholith post-dates the high-P metamorphism associated to continental collision, and may have been a source of heat and volatiles to the high-T metamorphism responsible for partial melting of the upper portions of the crustal section represented by the SGN. Two charnockitic rocks that show transitional contacts with granites of the Socorro batholith were also dated. The Socorro Charnockite is aged 641.6 ± 4.1 Ma, which overlaps those of regional orthogneisses (in part also of charnockitic character) considered as associated with a pre-collisional tectonics (subduction-related?). However, it is reported to transition to granites that are very similar to the HKCA granites of the Socorro batholith, which are yet undated. The Atibaia Charnockite has distinct geochemical affinity (lower mg# and Sr content; higher Zr), a younger age (633.3 ± 6.2 Ma), and may signal a different tectonic setting at the end of the period of plate consumption as yet poorly characterized.
KEYWORDS: zircon; U-Pb geochronology; SHRIMP; Socorro-Guaxupé Nappe; High-K calc-alkaline granite.
SHRIMP U-Pb Geochronology of the
Socorro Batholith and implications for
the Neoproterozoic evolution in SE Brazil
Bárbara Bueno Toledo1* , Valdecir de Assis Janasi1 , Luiz Gustavo Ribeiro da Silva1
DOI: 10.1590/2317-4889201820180040
ARTICLE
INTRODUCTION
One of the foremost features of the Neoproterozoic evo-lution of SE Brazil is the generation of voluminous granite magmatism of widely varied composition, whose ages spread for a large time interval (~800–500 Ma). Metaluminous, por-phyritic (hornblende)-biotite granitoids (dominantly monzo-granites, quartz monzonites and granodiorites) with I-type, high-K calc-alkaline (HKCA) character, are by far the most abundant granite type, and are the main components of some extensive batholithic masses with areas over 2,000 km2 (Fig.
1). Although the tectonic significance of these HKCA gran-ites is key to understanding the Neoproterozoic evolution of SE Brazil, their origin is still a matter of large uncertainties.
In fact, HKCA granites are known to be generated in various geodynamic environments (e.g., Barbarin 1999), occurring in both subduction-related and post-collisional settings. The occurrences in SE Brazil are usually associated in the literature to a continental-margin, subduction-related environment, in view of their huge volumes, deformed character and calc-al-kaline character (e.g., Heilbron et al. 2004, 2017, Janasi & Ulbrich 1991, Vinagre et al. 2014). However, some authors argue that the plutonic products of convergent tectonics may be restricted to older (> 640 Ma) granitoids that were largely converted to orthogneiss and migmatite (Hackspacher et al. 2003), and thus the bulk of the HKCA granites could be post-collisional (Meira et al. 2015). Precise dating and care-ful association with geological features related to plate-margin
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tectonics is thus key to correctly understanding the tectonic meaning of this magmatism.
Extensive geochronological surveys based on the U-Pb system in zircon and monazite by conventional TIMS have been carried out in some of the most expressive batholi-ths of SE Brazil, namely Três Córregos, Cunhaporanga (Gimenez Filho et al. 2000, Prazeres Filho et al. 2003) and Agudos Grandes (Janasi et al. 2001, Leite et al. 2007); more recently, in situ U-Pb dating of zircon by SHRIMP and LA-ICPMS was applied to the Serra da Água Limpa Batholith (Vinagre et al. 2014) and to the HKCA granites of the São Roque Domain (Janasi et al. 2016).
The Socorro Batholith is one of the most expressive occurrences of HKCA in SE Brazil, spreading out for over 1,200 km2 in the southern portion of the Socorro-Guaxupé
Nappe, and was the subject of several mapping and geoche-mical studies in the 1980’s that revealed a wide variety of granites which were grouped in different associations, inclu-ding, apart from the predominant HKCA porphyritic hor-nblende-biotite granites, several types of fractioned, pink granites, and also locally charnockites (Artur et al. 1993, Campos Neto et al. 1984a, Wernick et al. 1984a, 1984b). However, the geochronology of the batholith is restricted to determinations by the Rb-Sr system, which clearly results in unreliable ages (e.g., Tassinari 1988), and to two U-Pb zircon dates by TIMS reported by Topfner (1996) (629 ± 3 Ma) and Ebert et al. (1996) (610 ± 10 Ma), thus far con-sidered as the best estimates of the ages of the predominant HKCA granite magmatism in the Socorro Batholith.
As part of an ongoing re-study of the Socorro Batholith, we selected five representative samples of the three main granite associations recognized in previous works for U-Pb SHRIMP dating (Socorro I or Bragança Paulista association, corresponding to the predominant HKCA porphyritic hor-nblende-biotite monzogranite; Socorro II or Salmão, a pink, coarse-grained biotite syenogranite; and the Charnockite association; nomenclature by Artur et al. 1993 and Campos Neto et al. 1984a). Our results reveal a wide (> 30 M.y.) interval for the batholith construction, and suggest that the granite associations may have been generated in a succession that differs from what was previously admitted.
GEOLOGICAL SETTING
Tectonic setting
The Socorro-Guaxupé Nappe (SGN) is a giant allocth-tonous terrane constituted by migmatites and (in its basal portions) granulites intruded by large volumes of granites in the Neoproterozoic, and is interpreted as the root of a magmatic arc that was thrust over the southern margin
of the São Francisco Craton in the Ediacaran (Campos Neto & Caby 2000). Current tectonic models admit that the SGN exposes a continuous section of middle to lower crust that records events related to convergent tectonics which evolved from subduction to continental collision and finally was involved in post-collisional transtensional tectonics and then intruded by post-orogenic granites of A-type character (the Itu Granitic Province; Janasi et al. 2009). The post-collisional transtensional tectonics may be a reflection of the development of a younger oroge-nic belt located to the SE (the Ribeira Fold Belt, part of the Mantiqueira Province, an extensive Neoproterozoic-Cambrian orogenic system running parallel to the Atlantic coastline in Brazil (Heilbron et al. 2004, 2017). Geologic ter-ranes located immediately south of the SGN and related to the Ribeira Belt (Apiaí and São Roque domains) are also intruded by large volumes of “syn-tectonic” HKCA granites, and by post-orogenic granites of the Itu Granitic Province, which would thus straddle the limits between the SGN and Ribeira Belt. Some authors admit that the Apiaí and São Roque domains correspond, together with the SGN, to the reworked margin of a “cratonic” terrane (the Paranapanema lithospheric block of (Mantovani & Brito Neves 2005). Domains located further E-SE in the Ribeira Belt (e.g., the Oriental terrane, Fig. 1) also bear significant volumes of Neoproterozoic granites, but the most voluminous “syn-tectonic” batholiths are typically younger (e.g., Heilbron et al. 2013), as is the post-orogenic granite magmatism (520–500 Ma; Valeriano et al. 2016).
The SGN is admitted by several authors to be related to the evolution of the southern portion of the Brasilia Belt (Campos Neto & Caby 2000, Rocha et al. 2018). It would represent the active margin of Paranapanema Plate that was thrust over the passive margin of São Francisco paleocon-tinent (Campos Neto & Caby 2000) in a collisional set-ting. Orthogneisses dated by Hackspacher et al. (2003) at 660–640 Ma would represent arc magmatism that resulted from subduction of Neoproterozoic oceanic crust during early precollisional convergence and closure of a branch of either the Adamastor or Goianides paleo-ocean.
Neoproterozoic granitic magmatism
in Socorro-Guaxupé Nappe
Extensive elongated granitic batholiths of high-K calc--alkaline character are typical of both the Ribeira belt and the Socorro-Guaxupé Nappe. The tectonic context in which these rocks were formed is still ambiguous, being accepted as products of active continental margin magmatic arcs (Campos Neto et al. 1984a, Heilbron et al. 2004, 2013, 2017, Janasi & Ulbrich 1991, Trouw et al. 2013), or considered belonging to a post-collision environment (Meira et al. 2015).
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Large volumes of crustal granites throughout the crus-tal section are exposed in the Socorro-Guaxupé Nappe. Temperatures close to 1,000ºC were reached around 625 Ma in the deeper portions of Socorro-Guaxupé Nappe (at ~ 14 kbar), resulting in melting of depleted granulites and generation of charnockitic magmas (Janasi 2002). Similar age has been obtained for crustal granites generated at the temperature of biotite breakdown (~ 850ºC) by remelting of orthogneisses in the middle crust (biotite granite type Pinhal). At lower levels (in the southern portion of the Socorro Domain), garnet-biotite granites (Nazaré Paulista types), were generated by anatexis of paragneisses (or mixtu-res between ortho- and paragneisses), probably over a long period of time (ca. 25 M.y., between 635 and 610 Ma), as estimated by monazites dating in associated migmatites (Martins et al. 2009). Some large batholiths dominated by granitoids of high-K calc-alkaline occur in the SGN, Pinhal-Ipuiúna Batnolith (Haddad 1995) in the northern portion, and Socorro (Artur et al. 1993) and Serra da Água Limpa batholiths (Vinagre et al. 2014) in the southern portion.
Granites of Socorro Batholith
The Socorro Batholith corresponds to an extensive area elongated in the N30E direction in the southern portion of SGN dominated by granitic rocks (ca. 60 × 25 km; total ca. 1,200 km2) (Fig. 2).
The predominant lithology in the batholith is a porphyri-tic hornblende-biotite granite with up to 4 cm alkali felds-par megacrysts set in a medium to coarse-grained matrix, commonly foliated, with high color index (10–20), and monzogranitic to quartz monzonitic modal composition. These granites correspond to the Socorro I magmatism of Artur et al. (1993) and the Bragança Paulista suite of Campos Neto et al. (1984a) and are reported to be locally intruded by more felsic, pink to grey biotite granites, usu-ally inequigranular, coarse to medium-grained, attributed to “Salmão” suite (Campos Neto et al. 1984a) or Socorro II magmatism (Artur et al. 1993). Small bodies of orthopyro-xene-bearing, greenish granitoids (charnockites) occur in the northern portion of the batholith, where they are reported to transition into typical Socorro I granites (Artur 2003, Wernick et al. 1984a). Charnockites also form an isolated body in the southern part of the batholith, next to the city of Atibaia (Oliveira et al. 1994), where they seem to grade to pink, locally garnet-bearing granites.
Two U-Pb zircon ages are reported in the literature, and indicate ages between 629 ± 3 (Topfner 1996) and 610 ± 10 Ma (Ebert et al. 1996) for the predominant Socorro I granites; no reliable age determinations are available for the other granite types from the batholith. The country rocks of the batholith are orthogneisses and paragneisses usually affected by migma-tization. U-Pb zircon TIMS ages reported for the orthogneisses
AçD: Açungui Doman; CFT: Cabo Frio Terrane; CT: Curitiba Terrane; ET: Embu Terrane; Go: Goiás Magmatic Arc; LAM: Luiz Alves Microplate; OcT: Occidental Terrane; OrT: Oriental Terrane; SBB: South Brasília Belt; SGN: Socorro-Guaxupe Nappe; SRD: São Roque Domain
Figure 1. Tectonic framework of SE Brazil with the main tectonic domains (Janasi et al. 2016).
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are in 660–640 Ma range (Hackspacher et al. 2003), and are seen as an upper limit to the ages of the Socorro granites. A recent LA-ICPMS dating program in the Serra da Água Limpa batholith, which seems to correspond to an eastern continu-ation of the Socorro Batholith, dated similar HKCA granites in the 645–630 Ma range (Vinagre et al. 2014).
The Socorro Batholith is intruded by post-orogenic granitic plutons, which are part of the Itu Granitic Province, constitu-ted of granites of A-type or high-K calc-alkalinecharacter and associated basic bodies(Janasi et al. 2009). These rocks may be envisaged as an “inboard reflection” of orogenic processes occurring at the Mantiqueira Orogenic System (Janasi et al. 2009). Besides the most voluminous bodies (Itu, Atibaia
and Morungaba) the Guaripocaba stock is part of this pro-vince, and is intrusive in the area of the Socorro Batholith. The most robust ages for the Itu Province are ca. 580–570 Ma (Janasi et al. 2009), indicating that this magmatism occurred after a temporal hiatus, during which the SGN was raised.
METHOD
Whole-rock major and
trace-element analyses
X-ray Fluorescence was used to determine the major, minor and trace elements in whole rock samples. Large samples
Figure 2. Geological map of the Socorro Batholith (modified from Artur 2003) with location of dated samples.
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typically weighing 6–8 kg were broken into pieces of about 3–5 cm using hammer or hydraulic press, and then were crushed to fragments with an average size of 1.5 cm with a jaw breaker of Mn-steel. The material was then split in a cros-s-type Jones splitter, yielding 100–150 g sub-samples repre-sentative of the starting material. The sub-samples were then milled for 15 minutes on a Pulverisette-type planetary agate mill. This overall time is usually enough for the material to reach a particle size smaller than 74 microns.
Analyses were performed in a PANalytical AXIOS MAX Advanced spectrometer at the NAP-Geonalitica, Instituto de Geociências, Universidade de São Paulo, Brazil, following the protocol described in Mori et al. (1999). Major and minor elements were analyzed from molten tablets obtained from 1 g sample and 9 g of a mixture of spectroscopic grade lithium tetra and metaborate at 1,100–1,200ºC in a plati-num crucible, using a Claisse fusion machine. Trace elements were analyzed from pressed pellets obtained from homoge-nization of the pulverized sample (previously micronized in a McCrone Micronizer) and pressing to 30 ton with wax. Analytical quality was controlled using a reference material granite JG-1a from Geological Survey of Japan as an unk-nown sample, and duplicated samples. The values obtained should be within 2σ of the certified values, and the
dupli-cated samples within 1% of variation.
Rare earth and other trace elements were determined by ICPMS in a Thermo-Analitica ICAP quadrupode analyzer at the NAP-Geonalitica, Instituto de Geociências, Universidade de São Paulo, Brazil, following the protocol described in Navarro et al. (2008).
Approximately 40 mg of rock powder with grain size < 200 mesh were placed in a Teflon capsule Parr bomb and added with 5 mL of HNO3 and 15 mL of HF, both sub--boiling distillates. The material was heated to 200ºC in an electric oven, under pressure, for five days. The mate-rial was then cooled and transferred to a PFA beaker where the solution was heated in hot plate; in this process, SiF4 is eliminated by evaporation. After drying, the material is dissolved and transferred to a plastic bottle where weights were adjusted to 100 g with 1% HNO3. Analytical quality control was checked by the analyses of reference materials JG-1a and JR-1 as unknown, blank and duplicate samples. The values obtained should be within 2σ of the certified
values, and the duplicated samples within 1% of variation (Navarro et al. 2008).
Zircon concentration, mounting
and cathodoluminescence study
The separation and concentration of zircon consisted of crushing, grinding, sieving, vibrating table, electromag-netic separation, heavy liquids and finally manual picking.
The routine used at CPGeo is described by Sato et al. (2014) and consists of the following steps:
■ rock samples (0.5 to 3 kg for granites and ~ 20 kg for mafic rocks) are crushed in a jaw crusher;
■ crushed material is screened to separate a fraction of 100–250 mesh particle size, using a disk mill and a battery of sieves;
■ the separated fraction is taken to a vibratory table to concentrate heavy minerals;
■ magnetic minerals are removed with a hand magnet; ■ minerals with different magnetic susceptibilities are
concentrated in a Frantz-type magnetic separator, by varying the inclination and the intensity of the electro-magnetic field;
■ the least magnetic fractions are passed successively into bromoform (d = 2.85 g/cm3) and methylene iodide
(d = 3.2 g/cm3) to further concentrate the heavy minerals
of interest. Any remaining sulfides present in the concen-trates are eliminated with HCl or HNO3. About 50–100 zircon grains are separated by hand picking with the aid of a magnifying microscope, and then mounted on double sided adhesive tape and embedded in epoxy-type resin. The mount is then polished to expose the fresh surface of the grain trapped in the resin.
A previous study of cathodoluminescence (CL) images of each of the samples was necessary to choose the proper position of the spot during the pointed analyses by SHRIMP. After a thin layer of gold cover (2–3 nm) was added to the mounts, these images were obtained in a FEI Quanta 250 SEM spectrometer with a XMAX CL detector (Oxford Instruments). Operating conditions were: high voltage, 15 kV, distance, 16.9–17 mm, PMD detector, range of magnification, 95-250x.
U-Pb geochronology by SHRIMP
U-Pb zircon dating was performed in the SHRIMP IIe equipment installed at CPGeo, Instituto de Geociências, Universidade de São Paulo. The SHRIMP is a mass spec-trometer coupled to a high resolution ion microprobe that uses a collimated and accelerated beam of primary ions (O2) to reach a target where secondary ions are generated from 30-m spots. The secondary ions are accelerated through the equipment and the isotopes generated by the sample, 254UO +, 206Pb+, 207Pb+, 208Pb+, 238U + and + 254ThO and 196Zr2O+,
are measured successively. The corrections required by the technique are made by the analyses of unknown materials and reference materials with known isotopic ratios (matrix-mat-ched) for determining specific calibration factors (Black et al. 2004). 12–16 spot analyses from each of the unknown zircon samples are performed according to the method described
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in Sato et al. (2014). During the run of every 5 determi-nations analyzed, the Temora-2 reference material (estima-ted age 416.78 ± 0.33 Ma; Black et al. 2004) was used as
206Pb/238U age reference, for calculation of common Pb
rection factors and fractionation factors. Common lead cor-rections usually use 204Pb according to Stacey and Kramer
(1975). Reference material SL13 (238 ppm) is used as U composition reference. Data are reduced with SQUID 1.6 software (Ludwig 2009) and ISOPLOT 4 (Ludwig 2003) has been used for treatment of data to estimate ages and generate diagrams.
U-P
b ZIRCON DATING
Porphyritic hornblende-biotite
granite (Bragança Paulista-type, HKCA)
Sample petrography and geochemistry
The porphyritic hornblende-biotite granites of HKCA character correspond to the Bragança Paulista association, which are the most voluminous rocks in the Socorro Batholith. We chose two samples from localities in the northern and sou-thern portion of the batholith for U-Pb dating (Fig. 2), repre-senting compositions with different degrees of fractionation.
Sample BRP-08 is from the vicinities of the Pedra Bela hill, and corresponds to a porphyritic hornblende-biotite granite with high color index (~22), with abundant and very large K-feldspar megacrysts averaging 3–4 × 1.5–2 cm (Fig. 3A) set in a massive, coarse matrix where plagioclase occurs as the only feldspar.
Sample ATB-13 is from a road next to the SP-095, NW of Bragança Paulista; compared to BRP-08, this sample has lower color index (~15), and the K-feldspar megacrysts are a little smaller and more elongated (average 2–3 × 1 cm); a
slight solid-state foliation is evident, which is related to a ten-sional field and evidenced by the orientation of alkali feldspars. Our geochemical dataset of the Bragança Paulista type granites (Tabs. 1 and 2) shows that they are relatively primi-tive, with 60–66 wt% SiO2, mg#~40, combining relatively high contents of MgO (2.5–1.5 wt%), CaO (4.5–3.2 wt%) and Fe2O3 (6.2–4.3 wt%) with high K2O (3.8–4.6 wt%), Ba (1,000–1,600 ppm) and Sr (540–800 ppm). BRP-08 with 61.7 wt% SiO2 and 2.0 wt% MgO is among the most unfractioned compositions, while ATI-13 with 66.3 wt% SiO2 and 1.5 wt% MgO groups with the most felsic Bragança Paulista-type granites (Fig. 4). Both samples have moderately fractionated REE patterns (La/Yb)N = 24-30 and discreet negative Eu anomalies (Fig. 5), that are more pronounced in the least fractioned sample (BRP = 08; EuN/Eu* = 0.70, versus 0.83 in ATB-13 (Eu* = (Sm x Gd)½).
Zircon morphology and U-Pb dating
Zircon crystals from sample BRP-08 are elongated with aspect ratios from 4:1 to 5:1, and lengths up to 400 µm (Suppl. data). CL images show typical oscillatory zoning, which is more pronounced in darker zones where small inclu-sions that are white in CL are present. Lighter cores with less evident zoning and a thin CL-bright outer rim, sometimes truncating the oscillatory zoning, occur in some crystals.
SHRIMP results from 21 spots yield essentially concor-dant ages (typical discordance ≤ 4%; Tab. 3) which, howe-ver, spread over the concordia for ca. 50 M.y. (584–635 Ma, excluding three extreme results: the two youngest and the oldest one). The weighted average 206Pb/238U age (Fig. 6)
cal-culated by Isoplot is 610.1 ± 7.0 Ma(at 95% confidence), with a very high MSDW (6.1). Use of the Isoplot Unmix routine discriminates two age groups with 600.7 ± 3.9 Ma (eight samples) and 623.4 ± 4.8 Ma (six samples) (errors in calculated ages are reported as 2σ). A concordia age calculated
Figure 3. (A) Image of Bragança Paulista-type from the Pedra Bela hill. (B) Image of the dated sample of Salmão-type granite.
A B
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Table 1. Major and trace elements of granites from the Socorro Batholith by X-ray fluorescence.
Salmão
Granite Bragança Paulista Granite CharnockiteSocorro Atibaia Charnockite
BRP-03 BRP-06C BRP-13 BRP-06A BRP-06B BRP-07 BRP-08 BRP-09 BRP-10 ATB-13 BRP-11 BRP-12 ATB-06A ATB-08 BRP-05
SiO2 73.55 72.81 63.89 60.69 64.77 64.59 61.71 63.58 65.95 66.30 63.75 61.68 69.10 69.77 68.47
TiO2 0.22 0.45 0.87 1.18 0.862 0.93 1.15 1.17 0.89 0.80 1.15 0.92 0.53 0.46 0.54
Al2O3 13.34 13.30 15.23 15.77 14.63 14.74 15.15 14.85 14.74 14.61 14.92 16.22 14.46 14.66 14.23
Fe2O3 1.29 2.27 4.47 5.99 4.42 4.60 5.71 6.24 4.47 4.29 5.90 5.62 3.76 3.04 3.62
MnO 0.02 0.02 0.07 0.09 0.058 0.07 0.08 0.10 0.07 0.08 0.10 0.11 0.05 0.03 0.03
MgO 0.29 0.58 1.66 2.23 1.59 1.65 2.02 2.04 1.50 1.55 2.01 2.19 0.62 0.57 0.66
CaO 1.45 1.79 3.57 4.58 3.50 3.71 3.91 4.22 3.59 3.18 4.06 4.56 1.91 2.03 1.85
Na2O 2.81 2.32 3.09 3.19 2.82 2.64 3.10 2.94 2.95 2.94 2.97 3.09 2.79 2.81 2.83
K2O 5.22 5.39 4.59 4.08 4.80 4.54 4.63 3.58 4.44 4.70 3.67 3.76 5.76 5.88 5.73
P2O5 0.04 0.11 0.33 0.39 0.327 0.31 0.37 0.41 0.30 0.30 0.39 0.35 0.15 0.15 0.15
LoI 0.46 0.72 0.78 1.98 1.59 0.78 0.81 0.80 0.74 0.29 0.75 0.66 0.32 0.32 0.53
Total
(%) 98.68 99.76 98.56 100.16 99.37 98.55 98.64 99.93 99.64 99.029 99.67 99.16 99.45 99.722 98.63
Ba 541 1397 1350 1.600 1622 1581 1584 1.058 1290 1.340 1076 1.318 676 654 651
Ce 134 231 122 169 156 127 189 190 107 120 199 127 186 168 230
Co < 6 < 6 7 12 7 8 10 9 6 6 8 9 <6 < 6 < 6
Cr < 13 < 13 20 24 16 16 20 < 13 < 13 20 < 13 13 <13 < 13 < 13
Cu < 5 7 9 10 15 8 12 10 8 9 10 14 6 6 5
Ga 19 15 23 23 19 21 21 21 19 20 23 20 19 18 20
La 73 124 61 90 82 60 88 103 66 72 101 70 88 91 121
Nb < 9 < 9 18 14 11 17 20 19 13 15 18 14 13 12 11
Nd 41 57 50 62 51 60 75 67 40 37 73 49 58 53 73
Ni < 5 < 5 11 10 9 9 9 8 7 11 8 11 <5 < 5 < 5
Pb 30 21 19 18 13 16 19 15 18 20 14 20 18 25 17
Rb 183 118 153 126 134 135 153 126 131 157 130 111 166 168 176
Sc < 14 < 14 < 14 14 < 14 < 14 14 14 < 14 < 14 15 16 <14 < 14 < 14
Sr 183 643 681 783 748 678 658 542 626 647 544 799 141 170 162
Th 35 31 < 7 18 10 < 7 7 13 7 10 13 8 14 17 30
U 4 7 8 10 8 8 9 9 7 9 8 8 5 6 5
V 10 36 74 100 74 80 99 96 71 65 84 102 29 21 31
Y 5 8 28 21 17 28 31 32 19 18 29 26 16 11 9
Zn 22 30 65 90 69 73 89 90 67 62 86 74 50 41 54
Zr 159 197 250 271 254 261 318 341 223 252 328 231 415 402 397
Table 2. Rare earth and additional trace elements of granites from the Socorro Batholith by ICPMS.
Sample La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu Hf Pb Th U
BRP-03 75.83 134.69 14.23 44.21 6.25 1.13 2.75 0.33 1.24 0.18 0.39 0.05 0.31 0.05 4.70 33.05 36.17 1.56 BRP-08 86.71 174.14 20.68 76.57 12.59 2.31 8.16 1.06 5.58 1.05 2.75 0.39 2.39 0.33 8.45 17.44 5.70 0.89 BRP-12 65.47 129.80 14.32 52.26 9.04 2.13 5.84 0.83 4.52 0.85 2.24 0.33 2.04 0.29 5.40 17.08 6.74 0.42 ATB-08 84.28 160.27 17.37 56.65 8.39 1.34 4.09 0.56 2.45 0.42 1.01 0.12 0.69 0.10 8.73 20.61 14.31 0.71 ATB-13 65.27 120.23 13.26 45.41 7.85 1.76 5.18 0.71 3.50 0.64 1.62 0.23 1.36 0.20 6.80 18.64 9.08 0.89
ICPMS: inductively coupled plasma mass spectrometry.
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Figure 4. Geochemical variation diagrams for samples analyzed in this study and related samples.
Figure 5. Chondrite-normalized (Boynton, 1984) REE patterns of dated samples.
for the first set yields 599.5 ± 3.6(MSWD = 0.25) with a probability of fit of 0.62, while the concordia age for the second set is 620.1 ± 4.2 Ma, with higher MSWD (0.94) and lower probability of fit (0.33). No morphological or chemical differences exist between spots belonging to these two age groups, and some of the “older” dates correspond
to spots located at the border of zircon crystals. We prefer therefore to admit the weighted average age of the whole set of analyses as the best estimate of the magmatic crystalliza-tion of this sample, in spite of the higher associated MSWD. Indeed, the Unmix routine can yield any chosen number of populations, but in this case no clear age gap is observed when the whole set of data is considered and no chemical or textural contrast exists between the different spots.
Zircons from sample ATB-13 have varied morpholo-gies, with wide variation in aspect ratios, from 1.5:1 to 4:1 (Suppl. data). Most crystals are elongated, with lengths of 100–400 µm, and show oscillatory zoning, small granular inclusions of a CL-bright mineral, possibly apatite, occurring associated with some specific zones, and rare brighter cores. The shorter crystals show similar features, and more com-monly have corroded cores of varied texture; one CL-bright homogeneous core corresponds to an inherited crystal.
Fourteen spots were analyzed, and yield nearly concordant ages (≤ 5% discordant, with two exceptions, Tab. 3). Spot 13.1 is an inherited core with a concordant 207Pb/206Pb age of 1,445
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Sample
spot (commom) (%)Pb total
Pb
rad ppm
Th
ppm ppmU Th/U 207Pb/235U 1σ 206Pb/238U 1σ Rho 207Pb/206Pb 1σ
206Pb/238U
Age (Ma) 1s
207Pb/206Pb
(Ma) 1s Discordant%
ATB – 08 (Atibaia Charnockite) UTM: 74479343 x 36105 23 K
1.1 0.05 20 141 234 0.62 0.835 1.991 0.101 1.521 0.764 0.062 0.741 618 9 612 28 -1
2.1 -0.06 12 68 134 0.53 0.919 2.852 0.106 1.594 0.559 0.060 0.715 648 10 709 50 +9
3.1 0.35 30 102 336 0.31 0.874 1.807 0.105 1.496 0.828 0.064 1.440 645 9 613 22 -5
4.1 -0.08 25 125 270 0.48 0.900 2.551 0.106 1.721 0.675 0.060 0.669 648 11 666 40 +3
5.1 0.04 39 185 442 0.43 0.856 1.827 0.104 1.612 0.882 0.061 0.734 637 10 595 19 -7
6.1 0.03 10 58 115 0.52 0.868 3.199 0.104 1.956 0.612 0.061 0.813 637 12 624 55 -2
7.1 0.90 45 54 519 0.11 0.825 1.654 0.100 1.477 0.893 0.068 1.732 616 9 590 16 -5
8.1 0.13 37 197 422 0.48 0.862 1.732 0.103 1.487 0.858 0.061 0.957 634 9 622 19 -2
9.1 -0.04 46 90 513 0.18 0.861 1.630 0.104 1.476 0.906 0.060 0.665 636 9 609 15 -5
10.1 0.04 41 230 445 0.53 0.898 1.925 0.106 1.716 0.891 0.062 1.864 652 11 646 19 -1
11.1 0.60 6 54 72 0.78 0.840 4.896 0.101 2.263 0.462 0.066 1.371 619 13 620 94 +0
11.2 -0.05 29 116 331 0.36 0.859 1.794 0.103 1.498 0.835 0.061 0.879 633 9 617 21 -3
ATB – 13 Bragança Paulista UTM: 7464639 x 338956 23 K
1.1 -0.05 41 219 471 0.48 0.844 1.659 0.102 1.479 0.892 0.060 0.725 625 9 607 16 -3
2.1 0.79 32 145 370 0.41 0.869 2.102 0.101 1.493 0.710 0.067 0.772 618 9 697 32 +12
3.1 -0.06 83 618 950 0.67 0.834 1.567 0.102 1.459 0.931 0.060 0.485 624 9 586 12 -7
4.1 0.22 51 360 604 0.62 0.803 2.120 0.098 1.472 0.694 0.062 1.317 601 8 591 33 -2
5.1 -0.12 56 239 604 0.41 0.898 1.650 0.107 1.493 0.905 0.061 0.666 657 9 630 15 -4
5.2 0.66 52 445 611 0.75 0.819 3.338 0.100 1.479 0.443 0.066 1.784 612 9 589 65 -4
6.1 0.27 53 266 621 0.44 0.834 1.779 0.100 1.470 0.826 0.063 0.698 614 9 623 22 +2
7.1 0.28 38 209 447 0.48 0.804 2.012 0.098 1.628 0.809 0.062 0.691 603 9 585 26 -3
8.1 0.02 32 245 367 0.69 0.833 1.788 0.101 1.491 0.834 0.061 0.793 620 9 597 21 -4
9.1 -0.01 57 781 663 1.22 0.822 1.616 0.100 1.468 0.909 0.060 0.566 615 9 589 15 -5
10.1 0.52 47 234 575 0.42 0.783 2.273 0.096 1.502 0.661 0.064 0.818 591 8 573 37 -3
11.1 0.05 42 168 469 0.37 0.872 1.772 0.104 1.492 0.842 0.061 0.816 638 9 632 21 -1
12.1 0.83 55 584 665 0.91 0.799 2.233 0.096 1.474 0.660 0.066 0.683 590 8 620 36 +5
13.1 0.45 15 47 68 0.71 3.135 2.384 0.250 1.716 0.720 0.094 1.121 1439 22 1445 32 +1 Table 3. Results of U-Pb dating of Socorro Batholith zircon spots by SHRIMP. Results in color not used in age calculations.
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Sample
spot (commom) (%)Pb total
Pb
rad ppm
Th ppm
U
ppm Th/U 207Pb/235U 1σ 206Pb/238U 1σ Rho 207Pb/206Pb 1σ
206Pb/238U
Age (Ma) 1s
207Pb/206Pb
(Ma) 1s
% Discordant
BRP – 03 Salmão Granite UTM: 7456685 x 338634 23 K
1.1 -0.01 50.6 76 582 0.13 0.836 1.161 0.101 0.872 0.751 0.060 0.763 622 5 599 17 -4
2.1 0.03 52.2 140 600 0.23 0.847 1.306 0.101 0.889 0.681 0.061 0.772 622 5 627 21 1
3.1 0.01 106.0 125 1219 0.10 0.846 1.058 0.101 0.911 0.861 0.061 0.533 622 5 625 12 1
4.1 -0.01 43.1 98 486 0.20 0.858 1.230 0.103 0.906 0.736 0.060 0.830 633 5 616 18 -3
5.1 -0.02 127.9 778 1451 0.54 0.859 0.990 0.103 0.845 0.853 0.061 0.474 630 5 628 11 0
6.1 0.35 33.8 89 389 0.23 0.847 2.182 0.101 0.897 0.411 0.064 1.193 619 5 639 43 3
7.1 -0.09 13.4 38 60 0.64 3.716 3.427 0.262 2.173 0.634 0.102 1.833 1501 29 1675 49 12
8.1 6.14 4.0 56 43 1.30 0.890 26.819 0.100 2.218 0.083 0.114 8.213 616 13 754 564 22
9.1 -0.10 51.2 91 581 0.16 0.849 1.330 0.103 0.875 0.657 0.059 0.763 630 5 603 22 -4
10.1 0.01 36.6 105 440 0.24 0.823 1.362 0.097 0.890 0.653 0.062 0.988 595 5 665 22 12
11.1 0.01 43.9 86 505 0.17 0.853 1.613 0.101 0.883 0.548 0.061 1.231 621 5 648 29 4
12.1 0.03 40.6 71 152 0.47 4.654 2.157 0.311 1.808 0.838 0.109 1.139 1744 28 1777 21 2
13.1 0.22 218.8 414 3039 0.14 0.696 1.075 0.084 0.833 0.775 0.062 0.365 518 4 615 15 19
14.1 0.41 66.9 83 501 0.17 1.997 2.504 0.155 1.048 0.418 0.097 2.021 927 9 1502 43 62
15.1 0.59 18.6 47 204 0.23 0.879 3.961 0.106 0.996 0.252 0.065 2.005 647 6 618 83 -4
16.1 0.01 27.7 331 328 1.01 0.864 1.435 0.098 0.956 0.667 0.064 1.004 604 6 734 23 22
BRP – 08 Bragança Paulista UTM: 7479933 x 3350622 23 K
1.1 0.10 21.0 0.10 258 0.39 0.784 1.559 0.095 0.944 0.606 0.061 1.173 583.5 5.3 604 27 3
2.1 0.12 27.5 0.12 312 0.34 0.850 1.547 0.102 0.919 0.594 0.061 0.984 628.5 5.5 611 27 -3
2.2 1.91 13.9 1.91 172 0.70 0.754 7.938 0.092 1.367 0.172 0.075 3.599 568.7 7.4 578 170 2
3.1 0.18 17.7 0.18 209 0.66 0.804 2.217 0.099 0.984 0.444 0.061 1.292 606.6 5.7 570 43 -6
4.1 0.20 18.0 0.20 202 0.58 0.889 2.250 0.104 0.958 0.426 0.064 1.153 635.4 5.8 682 43 7
5.1 -0.12 14.7 -0.12 171 0.67 0.842 2.210 0.100 1.015 0.459 0.060 1.406 616.3 6.0 634 42 3
5.2 0.34 21.7 0.34 274 1.45 0.756 2.667 0.092 0.970 0.364 0.062 1.196 566.8 5.3 592 54 4
6.1 0.08 86.9 0.08 1001 0.31 0.831 1.094 0.101 0.859 0.786 0.060 0.602 620.1 5.1 592 15 -5
7.1 -0.06 26.3 -0.06 312 0.23 0.802 1.417 0.098 0.953 0.672 0.059 1.052 602.7 5.5 581 23 -4
8.1 0.16 43.0 0.16 525 0.91 0.775 1.490 0.095 0.899 0.604 0.060 0.829 586.5 5.0 567 26 -3 Table 3. Continuation.
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Sample
spot (commom) (%)Pb total
Pb
rad ppm
Th
ppm ppmU Th/U 207Pb/235U 1σ 206Pb/238U 1σ Rho 207Pb/206Pb 1σ
206Pb/238U
Age (Ma) 1s
207Pb/206Pb
(Ma) 1s Discordant%
9.1 0.08 23.6 0.08 271 0.84 0.845 1.765 0.101 0.982 0.556 0.061 1.132 621.2 5.8 626 32 1
10.1 0.18 13.8 0.18 164 0.50 0.811 1.890 0.098 1.017 0.538 0.062 1.436 600.6 5.8 612 34 2
11.1 2.20 11.2 2.20 131 0.57 0.809 8.604 0.097 1.171 0.136 0.078 3.094 598.9 6.6 614 184 2
12.1 1.27 14.9 1.27 178 0.52 0.800 5.567 0.096 1.065 0.191 0.071 1.283 590.6 6.0 619 118 5
12.2 0.06 56.8 0.06 671 0.29 0.820 1.309 0.098 0.869 0.664 0.061 0.739 605.5 5.0 619 21 2
13.1 0.62 18.1 0.62 208 0.93 0.837 3.051 0.101 0.999 0.327 0.065 1.250 619.1 5.9 611 62 -1
14.1 0.00 26.1 0.00 298 0.69 0.863 1.421 0.102 0.935 0.658 0.061 1.069 626.7 5.6 650 23 4
15.1 0.09 23.6 0.09 276 0.58 0.818 2.137 0.099 0.951 0.445 0.060 1.142 611.4 5.5 591 42 -3
16.1 0.75 22.9 0.75 272 0.64 0.805 3.562 0.097 0.946 0.266 0.066 2.077 597.4 5.4 609 74 2
16.2 0.17 81.9 0.17 963 0.36 0.816 1.223 0.099 0.861 0.703 0.061 0.581 607.4 5.0 599 19 -1
17.1 -0.14 26.8 -0.14 291 0.73 0.901 1.671 0.107 0.931 0.557 0.060 1.025 656.6 5.8 637 30 -3
BRP – 12 Socorro Charnockite UTM: 7504203 33458703 23 K
1.1 -0.03 28.3 142 328 0.45 0.850 1.367 0.101 0.915 0.669 0.061 1.004 617.6 5.4 651 22 5
2.1 0.14 38.0 168 447 0.39 0.840 1.551 0.099 0.883 0.569 0.063 0.816 607.3 5.1 662 27 9
3.1 0.01 44.1 531 499 1.10 0.869 1.457 0.103 1.133 0.778 0.061 0.828 631.4 6.8 649 20 3
4.1 0.14 17.5 46 203 0.24 0.834 2.787 0.100 0.994 0.357 0.062 1.325 615.0 5.8 618 56 1
5.1 0.15 11.1 8 122 0.06 0.874 2.138 0.105 1.073 0.502 0.061 1.763 646.0 6.6 608 40 -6
6.1 0.03 37.7 305 430 0.73 0.857 1.402 0.102 0.900 0.642 0.061 0.921 626.6 5.4 636 23 2
7.1 -0.03 35.7 173 397 0.45 0.874 1.291 0.105 0.897 0.695 0.060 0.898 641.9 5.5 624 20 -3
8.1 0.17 15.3 119 167 0.73 0.910 2.573 0.106 1.016 0.395 0.063 1.493 651.6 6.3 675 51 4
9.1 0.07 41.6 476 459 1.07 0.880 1.348 0.105 0.886 0.657 0.061 0.820 645.8 5.4 624 22 -3
10.1 0.05 8.7 119 95 1.29 0.936 4.122 0.106 1.178 0.286 0.064 1.823 651.3 7.3 738 84 13
11.1 0.01 46.9 293 513 0.59 0.899 1.203 0.106 0.879 0.731 0.061 0.779 652.0 5.4 647 18 -1
11.2 0.55 4.2 86 48 1.87 0.845 10.384 0.103 1.973 0.190 0.064 2.562 632.3 11.8 585 221 -8
12.1 0.00 58.0 289 619 0.48 0.918 1.107 0.109 0.865 0.782 0.061 0.689 667.1 5.5 641 15 -4
12.2 0.00 14.8 79 157 0.52 0.919 1.907 0.110 1.209 0.634 0.061 1.475 672.0 7.7 628 32 -7
13.1 0.15 15.2 268 169 1.63 0.871 1.817 0.104 1.014 0.558 0.062 1.372 640.7 6.2 620 33 -3
14.1 -0.01 28.0 146 320 0.47 0.837 4.749 0.102 4.627 0.974 0.059 1.039 625.3 27.6 588 23 -6 Table 3. Continuation.
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± 32 Ma. The remaining points spread over the Concordia for a relatively wide age range. The weighted average 206Pb/238U age
of all thirteen point results in a large error (615 ± 11 Ma) and high MSWD (4.2); together, these points do not yield a con-cordia. Excluding the two older results, which do not seem to be part of a continuous with the others, yields a weighted ave-rage 206Pb/238U age of 609.9 ± 8.4 Ma (at the 95% confidence
level) with MSWD = 2.1 and very low probability of fit (0.025) (Fig. 6). These spots yield a concordia age of 608.3 ± 6.6 Ma with MSWD = 2.2 and probability of fit = 0.14. This is con-sidered as the best age estimate of magmatic crystallization of sample ATI-13. A regression considering only the nine youn-gest results yields a slightly younger age (606.2 ± 5.5 Ma) with much lower MSWD (0.19) and higher probability of fit, but we see no criteria to exclude spots 1.1 and 3.1. The ages obtai-ned for the Bragança Paulista granite using the two different approaches are thus identical within error.
Porphyritic biotite-syenogranite
(Salmão-type)
Sample petrography and geochemistry
The porphyritic biotite-syenogranite corresponds to the Salmão association (Campos Neto et al. 1984a) or the Socorro II magmatism of Artur et al. (1993). These grani-tes form plutons in different portions of the batholith, with dimensions varying from 2 to 25 km2.
Sample BRP-03 was collected in the southern por-tion of the batholith (Fig. 2) and corresponds to an inequigranular porphyritic pink-colored biotite syeno-granite with a color index around 6 and alkali feldspar megacrysts measuring, on average, 4 × 1.5 cm (Fig. 3B). Accessory minerals include apatite, zircon, opaque mine-rals and monazite.
The geochemical data show high contents of SiO2 (73.6 wt%), K2O (5.2 wt%), Th (35 ppm) and U (4 ppm) (Fig. 7); mg# is ~30. In comparison to the other samples dated, it has the lowest contents of Fe2O3 (1.3 wt%), MnO (< 0.02 wt%) and MgO (0.3 wt%). The REE pattern is very fractioned, with (La/Yb)N = 166 with a negative anomaly of Eu (Eu/Eu* = 0.7) (Fig. 5).
Zircon morphology and U-Pb dating
Zircons from sample BRP-03 can be divided into two morphologically distinct populations. One has elongated prismatic shape with up to 300 µm length, and 3:1 aspect ratio. The cores are heterogeneous, without zoning or exhi-biting inconspicuous and irregular zoning, and are typically darker than rims. The other population has more rounded shapes and lengths up to 200 µm, with some cores, in CL images (Suppl. data), with a bright appearance.
Three cores yield inherited ages, but spot 14.1 is stron-gly discordant and will not be further considered. Spot 12.1 is 98% concordant, and yields a 207Pb/206Pbage of 1,777 ±
42 Ma; spot 7.1 is 12% discordant, and its 207Pb/206Pbage
is similar within error (1,675 ± 98 Ma).
Four of the other 13 points are > +10% discordant, and as such show 206Pb/238U that are too young. The remaining
nine spots yield a weighted average 206Pb/238U age (Fig. 6) of
626.6 ± 6.4 Ma with high MSWD = 2.4. Spot 15.1 has the highest age and is not part of a coherent age group with the other eight spots. Excluding it, the weighted average is 624.7 ± 3.6 Ma (2σ) with a lower MSWD (1.04) and a
probabil-ity of fit of 0.46. These eight samples yield a Concordia age (Fig. 8) of 624.4 ± 3.6 Ma(MSWD = 0.24), which is con-sidered the magmatic crystallization age of sample BRP-03.
Charnockites
Sample petrography and geochemistry
Charnockites were described as a marginal facies with transitional contacts to porphytic granites associated to the Socorro I magmatism nearby the city of Socorro (Artur 2003, Wernick et al. 1984a), occurring as elongated bodies with a maximum extension of 20 km. Sample BRP-12 was collected in this region, and is a foliated, porphyritic charnockite with dark green colour, and alkali feldspar as 2 × 1 cm megacrysts, and as a matrix mineral with pla-gioclase, quartz, orthopyroxene, clinopyroxene, biotite and hornblende.
The Atibaia Charnockite is a small NE-elongated body (3 × 0.5 km) in the southern portion of the Socorro Batholith (Fig. 2). Sample ATB-08 is medium- to coarse-grained, folia-ted, with greenish-brown color and monzogranitic com-position Mafic minerals are clinopyroxene, orthopyroxene, amphibole and traces of biotite; accessory minerals are zir-con, apatite and opaque minerals.
Our geochemical data (Fig. 4) shows important differences between the two charnockite occurrences. The Socorro charnockite sample is relatively primi-tive, and its geochemical signature is very similar to the Bragança Paulista-type granites, with 61.6 wt% SiO2, 4.6 wt% CaO, 2.2 wt% MgO and mg#~ 43, combi-ning relatively high contents of K2O (3.7%), Ba (1,300 ppm), Sr (800 ppm) and a fractionated REE pattern ((La/Yb)N = 82) with poorly developed negative Eu ano-maly (Eu/Eu* = 0.84) (Fig. 5). The Atibaia charnockite has higher contents of SiO2 (70 wt%), K2O (5.8 wt%), and Zr (402 ppm) and much lower Sr (170 ppm); the REE patterns are moderately fractionated ((La/Yb)N = 32.3) with a more pronounced negative Eu anomaly (Eu/Eu* = 0.62) (Fig. 5). This chemical signature is
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similar to neighboring garnet-bearing biotite granites (Fig. 5), and different from both Bragança Paulista and Salmão-type granites.
Zircon morphology and U-Pb dating
Zircon crystals from sample BRP-12 have different sizes and shapes, and can be divided into two populations, based
Figure 6. Weighted average of 206Pb/238U ages of dated zircon spots.
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on morphological and textured grain differences. The first is elongated, prismatic, with lengths of 200–350 µm; in CL images (Suppl. data), they show rims with oscillatory zoning and cores with dark gray to white shading. Crystals from the second population are 150–200 µm in length, with cores typically brighter (lower U) than the rims, some having a shiny appearance. In this case, the rims have lit-tle obvious zoning.
Sixteen points were analyzed and are ≤ 6 % discordant, with four exceptions that were excluded from age calcu-lations; spot 14.1 has a high analytical error and was also excluded (Tab. 3). The remaining 11 results spread along the Concordia for a wide time interval (206Pb/238U ages = 615–
667 Ma). As a result, the weighted average has a large error and MSWD (640 ± 11 Ma; 95% conf.; MSWD = 7.8), and no Concordia age is obtained from this set of data. Exclusion of the oldest and the two youngest 206Pb/238U ages defines a
coherent group of 8 samples, which yields a weighted aver-age (Fig. 6) 206Pb/238U age of 642.0 ± 7.7 Ma (95% conf.),
MSWD = 2.5 and probability of fit = 0.016. This group defines a Concordia age (Fig. 8) of 641.6 ± 4.1 Ma (2σ), MSWD =
0.5 and probability of fit = 0.48, which is considered the best estimate of the age of magmatic crystallization of the sample. Zircon crystals from sample ATB-08 are elongated, with rare rounded shapes, and lengths up to 420 µm. The cores present oscillatory zoning or are homogeneous, rarely with bright aspect and rounded formats in CL images (Suppl. data). In addition, some cores have inclusions and shades of dark gray or black. The rims may show some zoning.
Two out the 12 spots analyzed are > 5% discordant (-7 and +9%; Table 3). A weighted average 206Pb/238U age
obtained with all 12 spots yields 634.8 ± 5.6 Ma with MSWD = 1.5 and probability of fit = 0.11. A Concordia age can be obtained with all these results and yields 631.5 ± 6.7 Ma (95% confidence), with a much higher MSWD =
7.6 and very low probability of fit (0.006). Excluding the two results that are > 5% discordant yields a weighted aver-age 206Pb/238U age of 633.3 ± 6.2 Ma (2σ) with MSWD =
1.6 and probability of fit = 0.096. A Concordia age (Fig. 8) obtained from these 10 results yields an age of 630.3 ± 5.7 Ma, with high MSWD (5.1) and low probability of fit (0.024). All these ages are coincident within error; the weighted average (Fig. 6) 206Pb/238U age of 633.3 ± 6.2 Ma
is admitted as the best estimate of the age of this sample.
DISCUSSION
Age of granitic magmatism
in Socorro Batholith
Five samples of the most typical granite types of the Socorro Batholith were chosen for U-Pb dating by SHRIMP in this study. The samples consist of porphyritic granites related in previous works to the Bragança Paulista and Salmão suites (respectively, Socorro I and Socorro II associations of Artur et al. 2013) and two charnockites that form small occurren-ces described as transitional to granites from the batholith. The ages are interpreted as of magmatic crystallization and show a wide time interval, from early charnockites at ~642 Ma to high-K calc-alkaline metaluminous (biotite-hor-nblende) granites (Bragança Paulista-type) at ~610 Ma, i.e., a minimum 30 M.y. interval for the build up of the batholith.
The five ages obtained here seem part of a continuum and suggest a chronological sequence from the Socorro Charnockite (641.6 ± 4.1 Ma) to the Atibaia Charnockite (633.3 ± 6.2 Ma),Salmão-type granite(624.4 ± 3.6 Ma), and then the Bragança Paulista-type granites (610.1 ± 7.0 Ma and 608.3 ± 6.6 Ma). This sequence contradicts some of the assumptions made in the literature.
The Socorro Charnockite is described as transitional with the Socorro I (Bragança Paulista-type) granites and yet has a much older age. It is possible that the granites described as transitional to the Socorro Charnockite (which remain so far undated) are indeed of the same age, and in fact their geochemical signature (Wernick et al. 1984a) is very similar to the Bragança Paulista type granites, but our data suggest that the Socorro charnockites (and eventually their opx-free equivalents) may belong to an older association.
The fact that the dated “Salmão-type” granite is older than the two Bragança Paulista type granites may appear surprising, since this type of granite is reported as younger in the literature (“Socorro II” association), based on field work (Artur et al. 1993, 1994, 1996, Wernick et al. 1997, Wernick & Menezes 2001, Artur 2003, Campos Neto et al. 1984b). Again, older HKCA (Bragança Paulista-type) grani-tes may exist, and this is clear from the U-Pb zircon TIMS
Figure 7. Geochemical variation diagram Th vs. U. of dated samples.
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Figure 8. Concordia ages of dated samples, with an additional figure from sample BRP-03 indicating the points with inherited ages. Data for BRP-08 do not yield a Concordia age, and in this figure only the graph with age distribution are shown.
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age reported by Topfner (1996) for a sample with typical Bragança Paulista affinity (629 ± 3 Ma). While the scrutiny of the data for this sample in the original work does not show any suggestions that a different interpretation could be offered for its age, we observe that some other ages repor-ted in that work were shown to be ~20 M.y. older than the ages obtained for the same plutons in a recent SHRIMP and LA-ICPMS dating program (Janasi et al. 2016), and this was attributed to the presence of tiny inclusions of inherited zircon in the multigrain fractions used in the TIMS study. Our ages for the two Bragança Paulista-type granites are identical within error, and coincide with the age reported by Ebert et al. (1996) to a sample collected in the southe-astern portion of the batholith (610 ± 10 Ma).
Except in sample BRP-03 (Salmão-type granite), inheri-tance is uncommon in the studied samples; in fact, no inhe-rited zircon was identified in the two charnockite samples and a single one was found in one of the Bragança-Paulista type granites (BRP-13). This suggests that the effect repor-ted by Janasi et al. (2016) in the São Roque granites should not be effective here. The spread of ages over the concor-dia for up to 50 M.y. (also recorded in similar granites in the region, see for instance Vinagre et al. 2014) may reflect other two causes: the presence of antecrysts (i.e., crystals from the same magmatic system previously crystallized and cannibalized by the magma that formed the dated pulse) or slightly younger lead-loss events (as demonstrated by several recent reports of U-Pb zircon ages dated by TIMS after chemical abrasion; e.g., Almeida et al. 2018). At the moment, we cannot detect these effects, and thus we admit that both may respond for part of the spread. TIMS dating of selected crystals after chemical abrasion would certainly be a valuable tool to further improve the geochronology of some samples.
Correlations with other batholiths
of HKCA affinity in SE Brazil
The Socorro Batholith is one of the major expressions of Neoproterozoic granitic magmatism in SE Brazil and is com-parable in volume to other important batholiths dominated by HKCA granites such as Agudos Grandes, Três Córregos, Cunhaporanga and Serra da Água Limpa. Figure 9 compa-res the ages obtained in this work with data obtained by the U-Pb method in zircon for these batholiths.
Only recently in situ methods (SHRIMP and LA-ICPMS) have been used to date these granites, and as reported by Janasi et al. (2016), at least in the case of the granites from the São Roque Domain, the new in situ results have shown systematically younger ages, which raised the suspicion that some ages obtained by TIMS may be older than the true magmatic age (by as far as
20 M.y.) due to the presence of tiny inclusions of inherited zircon in multigrain fractions used for dating. A similar situation was observed in the geochronology of HKCA granites from the Três Corregos and Cunhaporanga gra-nites, where part of the U-Pb TIMS ages older than 610 Ma presented in preliminary reports (Prazeres Filho et al. (2003) were revised to younger values (610–590 Ma) after SHRIMP dating (Prazeres Filho 2006). In fact, impor-tant amounts of zircon inheritance are reported in sam-ples of HKCA granites from these batholiths, particu-larly those intruding metasedimentary sequences in the Ribeira Belt (Três Córregos, Cunhaporanga and Agudos Grandes (e.g., Gimenez Filho et al. 2000, Janasi et al. 2001, Prazeres Filho et al. 2003, Leite et al. 2007), and in situ methods seem more adequate to obtain their true age of magmatic crystallization.
Figure 9 shows that the best estimates of magmatic crystallization ages available for HKCA granites from the Ribeira Belt indicate that the greatest volume of these granites was generated in the 610–590 Ma period. In the Agudos Grandes batholith, Leite et al. (2007) sugges-ted that the typical HKCA granites forming elongasugges-ted intrusions are slightly older than equivalents more con-taminated with middle crust material that form plutons with subcircular shape in plant, referred to as “late-o-rogenic”, whose ages are in the 605–600 Ma interval. In the São Roque Domain, typical HKCA granites also tend to be slightly older than occurrences with peralu-minous or subalkaline character dated at ~590 Ma (Janasi et al. 2016).
Age determinations for the HKCA magmatism in the Socorro-Guaxupé are less abundant in the literature, and the results of LA-ICPMS U-Pb dating reported for the Serra da Água Limpa Batholith by Vinagre et al. (2014) indicate an older interval for the HKCA granite magmatism (645–630 Ma; Fig. 9). This partly overlaps the range of ages determined for the migmatitic orthogneisses admitted to be subduction-re-lated by Hackspacher et al. (2003) (660–640 Ma). Our new data indicates that important volumes of Bragança Paulista-type granites were generated at ca. 610 Ma in the Socorro Batholith (see also the age reported by Ebert et al. 1996), i.e., contemporaneous with the peak of HKCA magmatism in the nearby (Apiaí and São Roque) domains of the Ribeira Belt.
Inferences on sources and
tectonic environment
A reassessment of the petrogenesis of the southern part of the Socorro Batholith is the subject of a cur-rent project using additional elemental and isotope geochemistry data, and is not the focus of the present article. A few considerations can be made considering
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the whole-rock geochemical and geochronological data presented here.
The oldest age obtained here is that of the Socorro Charnockite, which has a HKCA geochemical signature very similar to the Bragança Paulista-type granites. These dry, high-temperature, relatively primitive (~62 wt% SiO2) are not typical products of partial melting of the continental crust, and may have connections with mantle-derived basic magmatism, which is also suggested by the common pre-sence of mafic enclaves.
The age obtained for the Atibaia Charnockite is ca. 10 Ma younger, and the chemistry of this rock (and also of associa-ted granites, Fig. 4) is indeed indicative of a different source and perhaps also of a change in tectonic setting. The rela-tively low mg# ~ 27 combined with high Zr (~400 ppm) and low Sr (< 180 ppm) is indicative of a non-calc-alkaline character, and perhaps a closer affinity to the São José do Rio Pardo mangerite-charnockite association present in the northern part of the NESG and dated at 623.3 ± 3.1 Ma (Janasi 2002).
The high-grade metamorphism that affected the metasupracrustal sequences of the SGN has been shown to have lasted for a period as long as 25 M.y., between
635 and 610 Ma, based on U-Pb and chemical dating of monazite and zircon from migmatites (Martins et al. 2009, Rocha et al. 2017). This coincides with the range of ages of the Socorro granites, with the possible exception of the Socorro Charnockite. The Atibaia Charnockite may be a product of partial melting of a dry, granuli-tic source, during this high-grade metamorphism, as suggested for the São José do Rio Pardo association. Similarly, the fractionated (~ 73 wt% SiO2) Salmão-type granite dated here is probably a product of crustal melting, as suggested by its moderately peraluminous character, trace-element signature (e.g., high Th and LREE contents) and abundance of inherited zircon. Indeed, it shares important compositional attributes with the regional anatectic granites of Nazaré Paulista type, and is coeval with the oldest occurrences of these granites (e.g., 623.6 ± 1.6 Ma; U-Pb TIMS monazite age reported by Janasi (1999).
The ~610 Ma ages determined for the Bragança Paulista-type HKCA granites (this work; Ebert et al. 1996) indicate that their emplacement was coeval with the late stages of regional high-grade metamorphism which is associated to partial melting of fertile crustal protoliths, possibly under
Figure 9. Timing of granite magmatism in Socorro Batholith compared with other major granite batholiths Três Córregos, Cunhaporanga, Serra da Água Limpa, Agudos Grandes and São Roque Domain. Data sources and names of the occurrences in Table 4.
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Table 4. Results of U-Pb isotope determinations of Três Córregos, Cunhaporanga, Serra da Água Limpa, Agudos Grandes and São Roque Domain.
Sample Unit Rock type Mineral Analytical Method Age Error Reference
Socorro Batholith
1. BRP – 12 Socorro
Charnockite Charnockito Zircon SHRIMP 641 4 This study
2. ATB – 08 Atibaia
Charnockite Charnockito Zircon SHRIMP 633 6 This study
3. BRP – 03 Salmão Bt syenogranite Zircon SHRIMP 624 4 This study
4. ATB - 13 Bragança
Paulista Bt syenogranite Zircon SHRIMP 608 6 This study
5. BRP – 08 Bragança
Paulista Hbl-bt granite Zircon SHRIMP 610 7 This study
6. H3 Bragança
Paulista Granite Zircon TIMS 610 10 Ebert et al. 1996
7. Bragança
Paulista Granite Zircon TIMS 629 3 Topfner 1996
8. H621 Piracaia Milonitic
granitic gnaisse Zircon TIMS 642 1
Hackspacher
et al. 2003
9. H705B Piracaia Orthogneiss Zircon TIMS 653 13 Hackspacher
et al. 2003
10. H623A Paraisópolis
Complex Granulite Zircon TIMS 646 7
Hackspacher
et al. 2003
Serra da Água Limpa
10. RDTM 62 Facies 3 Porphyritic
granite Zircon LA-ICPMS 667 10 Vinagre et al. 2014
11. RDPA 44 (SALB) Facies 3 Porphyritic
granite Zircon LA-ICPMS 645 5 Vinagre et al. 2014
12. RDPA 46 (SALB) Facies 3 Porphyritic
granite Zircon LA-ICPMS 630 12 Vinagre et al. 2014
13. VAC 10 (SALB) Facies 4 Porphyritic
granite Zircon LA-ICPMS 631 7 Vinagre et al. 2014
14. RDIT 41 (SALB) Facies 5 Qtz-syenite Zircon LA-ICPMS 634 8 Vinagre et al. 2014 Agudos Grandes
15. PD - 313f Turvo Ms-Bt
leucogranite Monazite TIMS 610 1 Janasi et al. 2001
16. PD - 526 Ibiúna Hbl-Bt
monzogranite Zircon TIMS 610 2 Janasi et al. 2001
17.PD - 462 Piedade Ms-Bt granite Monazite TIMS 601 2 Janasi et al. 2001
18. PD - 474b Piedade Bt granite Zircon TIMS 604 8 Janasi et al. 2001
19.PD - 420 Piedade Bt granite Zircon TIMS 605 7 Janasi et al. 2001
20.PD - 498 Roseira Bt granite Monazite TIMS 600 4 Leite et al. 2007
21.PD - 2266 Serra dos Lopes Bt granite Monazite TIMS 604 3 Leite et al. 2007
22.PD - 2154 Pilar do Sul Ms-Bt granite Monazite TIMS 600 4 Leite et al. 2007 Três Córregos (E)
23.E - 3 Barra do Chapéu Foliated granite Zircon TIMS 610 3 Gimenez Filho et al . 2000
24.MN - 15 Barra do Chapéu Hbl-Bt
orthogneiss Zircon TIMS 608 5
Gimenez Filho
et al. 2000
25.S - 1 Saival Hbl-Bt granite Zircon TIMS 605 2 Gimenez Filho
et al. 2000
Continue...
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Table 4. Continuation.
SHRIMP: Sensitive High Resolution Ion Microprobe ; TIMS: Thermal Ionization Mass Spectrometry ; LA-ICPMS: laser ablation inductively coupled plasma mass spectrometry.
Sample Unit Rock type Mineral Analytical Method Age Error Reference
Três Córregos (W)
26. HP - 06 Paina Hbl-Bt tonalite Zircon SHRIMP 645 10 Prazeres Filho 2005
27.HP - 07 Arrieiros - Cerro Azul
Hbl-Bt
granodiorite Zircon SHRIMP 610 3
Prazeres Filho 2005
28.HP - 121 Arrieiros -
Cerro Azul Granodiorite Zircon TIMS 617 2
Prazeres Filho
et al. 2003
29.HP - 44 São Sebastião Hbl-Bt qtz
monzonite Zircon SHRIMP 601 22
Prazeres Filho 2005
30.HP - 44 São Sebastião Hbl-Bt qtz
monzonite Zircon TIMS 604 4
Prazeres Filho
et al. 2003
Cunhaporanga
31.HP - 03 Ribeirão Butiá Monzogranite Zircon TIMS 591 3 Prazeres Filho 2006
32.HP - 437 Ribeirão Butiá-Pitangui
Qtz-monzodiorite Zircon SHRIMP 601 7
Prazeres Filho 2006
33.HP - 21 Piraí do Sul Monzogranite Zircon TIMS 601 7 Prazeres Filho et al . 2003 São Roque Domain
34. SR -07 São Roque Monzogranite Zircon SHRIMP 604 3 Janasi et al. 2016
35.MD42B Cantareira Syenogranite Zircon SHRIMP 592 4 Janasi et al. 2016
36.MD24 Fazenda Itahyê Monzogranite Zircon SHRIMP 598 4 Janasi et al. 2016
37. JP-18 Vila dos
Remédios Qtz-syenite Zircon SHRIMP 590 4 Janasi et al. 2016
38. TICO-2 Tico-Tico Granite Zircon LA-ICPMS 591 4 Janasi et al. 2016
39. CANT-6 Cantareira Granite Zircon LA-ICPMS 599 4 Janasi et al. 2016
40.TAP-1 Taipas Granite Zircon LA-ICPMS 602 6 Janasi et al. 2016
41.ITQ-2 Itaqui Granite Zircon LA-ICPMS 594 5 Janasi et al. 2016
water-fluxed regime (Martins 2006). It can therefore be speculated that the intrusion of large volumes of high--temperature, relatively primitive, HKCA granites may be in part responsible for the influx of heat and volati-les that facilitated widespread melting in the upper levels of the presently exposed crustal section of the SGN. The young ages of these Bragança Paulista-type granites seem difficult to reconcile with models that admit a pre-collisio-nal setting for the HKCA magmatism, and indeed high--pressure metamorphism diagnostic of collisional setting is, at least in part, older (Reno et al. 2009). The evolved isotope signature and enriched geochemical signature of these HKCA granites is indicative that they are, at least in part, the products of crustal recycling. The few inheri-ted zircon cores identified in this work show ~1.4-1.8 Ga ages that overlap the Sm-Nd model ages reported for the SGN (e.g., Janasi 1999), which is consistent with the idea that the reworked crust is distinct, and younger, than that
forming the nearby Apiaí and São Roque Domains in the Ribeira Belt.
CONCLUSIONS
Our U-Pb zircon SHRIMP dating program determined the ages of the main components of the Socorro Batholith, a major component of the allochtonous Socorro-Guaxupé Nappe. Two samples of HKCA porphyritic biotite-hornblende granites of relatively primitive (60–67 wt% SiO2) that are the most voluminous component of the batholith were dated, and yielded similar results (Pedra Bela sample BRP-08 in the nor-thern portion of the batholith, 610.1 ± 7.0 Ma and Bragança Paulista sample ATB-13 in the southern portion, 608.3 ± 6.6 Ma). These ages are similar to U-Pb zircon ages recently obtained by in situ methods in similar rocks (HKCA grani-tes) in other large batholiths in neighboring domains (Apiaí
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and São Roque) from the Ribeira Belt, but younger than the U-Pb zircon LA-ICPMS ages reported for the HKCA granites of the Serra da Água Limpa Batholith, located immediately east of the Socorro batholith (645–630 Ma).
A more fractioned (> 72 wt% SiO2) “Salmão-type” gra-nite reported in the literature as related to a younger event (“Socorro II magmatism”) yielded a precise age that is cle-arly older (624.4 ± 3.6 Ma) than the two HKCA samples. This age is similar to that of the oldest anatectic granites and migmatites that were produced during a prolonged period of high-grade metamorphism (635–605 Ma) that affected the SGN. Our data thus indicates that at least part of the HKCA magmatism of the Socorro batholith post-dates the high-P metamorphism associated to continental collision, and may have been a source of heat and volatiles to the high-T metamorphism responsible for partial melting of the upper portions of the crustal section represented by the SGN.
Two charnockitic rocks that show transitional contacts with granites of the Socorro batholith were also dated. The Socorro Charnockite has an age of 641.6 ± 4.1 Ma, which overlaps those of regional orthogneisses (in part also of charnockitic character) considered as associated with pre-collisional tec-tonics (subduction-related?). However, it is reported to tran-sition to granites that are very similar to the HKCA granites
of the Socorro Batholith, which are yet undated. The Atibaia Charnockite is younger (633.3 ± 6.2 Ma) and has distinct geochemical affinity (lower mg# and Sr content; higher Zr), which may signal a different tectonic setting at the end of the period of plate consumption as yet poorly characterized.
ACKNOWLEDGEMENTS
Financial support for this work was provided by Fapesp through Grant 2015/01817-6 (to VAJ). LGRS acknowle-dges a Scientific Initiation scholarship by CNPq. VAJ is a CNPq Productivity Researcher (Grant 305661/2014-0). Kei Sato at CPGeo is acknowledged for qualified support in obtaining and processing geochronological data. A care-ful review by Claudio Valeriano, Stefano Zincone, Rodrigo Vinagre and the associated editor Umberto Cordani were very helpful to improve the manuscript.
SUPPLEMENTARY DATA
Supplementary data associated with this article can be found in the online version: Supplementary data A1-A5.
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